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NGT 57 2 121-131.Pdf THREE FOLD PHASES IN THE NORTHERN PART OF TROLLHEIMEN IN THE NORWEGIAN CALEDONIDES* FREDRIK LØSET Løset, F.: Three fold phases in the northern part of Trollheimen in the Nor­ wegian Caledonides. Norsk Geologisk Tidsskrift, Vol. 57, pp. 121-131. Oslo 1977. The northern border of Trollheimen towards Surnadalen has a complex ge­ ology with Cambro-Silurian, Eo-Cambrian (?) and Precambrian rocks folded three times during the Caledonian orogeny. The first recognizable folds, F1, are isoclinal slip folds associated with a pervasive axial plane schistosity and lineation. The Surnadal syncline and other major recumbent folds in the northern part of the area belong to the first phase of folding. The second folds, F2, are rather tight flexural-slip folds, while the third folds, F3, are open flexural-slip structures. A regional dome structure with Precambrian granitic gneisses in the core occurs in the south-western part of the area. F. Løset, Norges geotekniske institutt, P.O.Box 40, Tåsen, Oslo 8, Norway. Trollheimen is the mountainous region between Oppdal and Surnadal in north-western Norway. In the central part of Trollheimen there are mostly basal gneisses of Precambrian age. In the Oppdal district there are flag­ stones, micaschists, and some volcanic rocks of presumably Eo-Cambrian to Cambro-Silurian age above the gneisses. In the Surnadal district a wedge of Cambro-Silurian rocks has been folded down into the basal gneisses. This is the Surnadal syncline. The geology of Trollheimen has been investigated by several geologists. Strand (1953) described the rocks in the Surnadal syncline. He mapped a zone of quartzite in the boundary zone between the basal gneisses and the overlying micaschists. This quartzite was therefore regarded to be of Eo­ Cambrian age, belonging to the Tingvoll Group of Hernes (1956a). SrjRb­ dating from the basal gneisses in this district gave 1600-1800 mill. years (Priem 1967). It is, however, not established that the boundary between the Precambrian and the Cambro-Silurian follows the quartzite zone, and the Eo-Cambrian age of the quartzite is uncertain. In his papers, Hernes (1956a, b) gave several profiles across the Surnadal syncline, describing the syncline as a large isoclinal, recumbent fold. Large recumbent folds have also been described from this region by other geolo­ gists. Muret (1959) distinguished four tectonic phases here: The piling up of several recumbent folds or nappes. Subsequent folding of these nappes. 122 F. LØSET Formation of a large culmination which gave rise to local folds by down­ ward gliding from the culmination. Formation of N-S fractures. In the Oppdal district, large recumbent folds were described by Holtedahl (1950), and in the Lesja area Scott (in Strand & Kulling 1971) described two phases of falding. From the central part of Trollheimen, Hansen (1967, 1971) made detailed investigations. The rocks here have been deformed into a large scale recumbent nappe, which has later been deformed into broad upright domal antiforms and tight basins. The object of the present paper is to describe the folds of the different fold phases and to discuss the falding history of the area. General geology The investigated area is in the northern part of Folldalen, which is a hang­ ing valley from south to Surnadalen. Fig. l is a geological map of the area. The youngest rocks are a series of micaschists and amphibolites. The north­ ernmost zone of these rocks belongs to the Surnadal syncline and is there­ fore probably of Cambro-Silurian age, and the rocks are probably similar to the Gula Group. Rocks of the same type further to the south in the area are estimated to be of the same age. Most of the amphibolite is probably supracrustal but numerous thin beds may be sills. In the northern zone of micaschists and amphibolite, there is a zone of augengneiss with mylonitic groundmass and augen of microcline. This may be a thrust-zone. Above this zone there occur thick beds of amphibolite with numerous trondhjemitic intrusions, but below there are only thin: amphibolite beds, and trondhjemite seems to be missing. At the base of the Cambro-Silurian sequence there is an arkosic to quart­ zitic schist which varies in thickness due to isoclinal falding. This rock is lithologically similar to the light sparagmites of Oppdal, Gudbrandsdalen etc. for which an Eo-Cambrian age has been suggested. In the underlying gneiss there are numerous sills and dykes of granite which are not observed in the arkosic schist. The arkosic schist therefore seems to be younger than the gneiss. The basal gneiss is of Precambrian age as the Sr/Rb-dating gives 1600- 1800 mill. years (Priem 1967). In the northern part of the area the composi­ tion of the gneiss is mostly granitic and at the boundary to the arkosic schist there is a zone of augengneiss. This augengneiss has a granitic to granodio­ ritic composition but not a my1onitic groundmass as the augengneiss in the Cambro-Silurian rocks. In the southern part of the area the gneiss usually has a dioritic to quartz-dioritic composition, but in Tinnfjellet there is a rather homogeneous granitic gneiss. In the gneiss there are numerous intru- Fig. l. Geological map of the northem part of Trollheimen. - - --- --- --- - -- --------- -- --- --- -- -- ?J --- 3!l - --- ---- T INNFJELLET Scale / o 2 3 60 LEGEND Mica 5ehist and amphibolite � ( Cambro-Silurian) � Arkosic schist} (Eo-Cambrian?) Gneiss � Precambrian � Augengneiss L, (F, axes) -- F2 axes s, ( fol iation ) Possi ble thrustzone 124 F. LØSET sions of different character. There are at !east two generations of granitic intrusions and basic intrusions of different compositions. All the rocks are metamorphosed to the almandine-amphibolite facies. Three phases of folding Structurally the area is divided in two parts. The northern half belongs to the Surnadal syncline and similar ENE-WSW or E-W structures. The southern part Tinnfjellet forms a dome surrounded by arkosic schist. At least three phases of folding can be distinguished. In the northern part of the area all fold axes have a direction about E-W. In Tinnfjellet the axial direction varies (Fig. 1). The small structures are best preserved in the ar­ kosic schist. First folds (F1) The oldest planar structure is a lithological banding S0 which has been de­ formed into isoclinal folds, F1• The F1 fold amplitudes are much longer than their wave-lengths (Fig. 2). These are typical similar-type folds with tight closures and a pervasive axial-plane schistosity, S1, which is the main schisto­ sity in this area. The main schistosity is therefore not folded by F1• A linea­ tion L1 is of F1 age and is defined as the line of intersection of S0 and S1. The F1 axes (and L1) have a direction about E-W in the northern part of the -=---��i�� - � - -- =- - - ------- - - -- - -- - ....._;:::--=-� =��-· -. -- -- --- _s, - --:::.. -==- -=- - �- -- Fig. 2. Profiles of F 1 folds. THREE FOLD PHASES IN NORTHERN PART OF TROLLHEIMEN 125 F2- folds F3- fold Fig. 3. Profiles of F2 and F3 folds. area. In the southern part of the area the F1 linear structures have variable orientations. Second folds (F2) The schistosity S1 is laid in folds where the limbs have almost the same or­ thogonal thickness, e.g. essential flexural-slip folds. These are termed F2 folds. Slight thinning of the fold limbs has taken place locally, and in some localities a weak axial plane schistosity (S2) can be observed. The F2 folds are rather tight, but usually not isoclinal; the closures are rounded and the fold amplitudes are of the same length as the wave-lengths (Fig. 3). In the northern part of the area the F2 axial direction is about E-W, parallel to the F1 axes. In the southern part of the area the F2 axes are tangential to the dome structure and usually different from the F 1 axial direction. The axial planes of the F2 folds vary in attitude due to late F3 falding. A lineation L2 occurs sometimes, in part defined as the axes of the microfolds; and mul­ lions and boudinage struct�res may belong to the same phase of falding. Third folds (F3) The youngest folds, F3, are open flexural-slip folds with amplitudes slightly less than their wave-lengths (Fig. 3). They are only rarely associated with lineation and the axial directions are always approximately E-W with axial plane nearly vertical. The three types of folds here described are not identical with the three fold types described by Hansen from the central part of Trollheimen (Han­ sen 1971). The 'sahlfolds' and 'norfolds' of Hansen are both similar type 126 F. LØSET N l l ----- ----') / s .,. / l Surnadal ---......../ / l --- / / / l / / // l l // / / Tinnfjel let o 2 3 km �- Mi ca se hist and amphibolite 1:.,;.,, Augengnei ss [�::·.:\��:·;�! Arkosic schist l� Gneiss Fig. 4. A) Projection of the geological structures into a vertical N-S-striking plane. B) Profile of the Surnadal syncline (after Hernes 1956 a). folds, but they do not seem to be identical to the F1 folds in the northern part of Trollheimen. The F1 folds may be older than Hansen's folds. Han­ sen also mentions some still older folds but gives no description of them. Hansen's 'discfolds' have a parallel type of geometry and may be identical to the F2 folds. Major recumbent folds The northern part of the area is dominated by the Surnadal syncline. The syncline is nearly recumbent and isoclinal (Hernes 1956a, b). Above the re­ cumbent syncline there seems to be another recumbent fold with closure to . the north and with gneiss in the core (Figs. 4 and 5). Most of the rocks in the northern part of Folldalen belong to the upper limb of the syncline; the overlying recumbent fold and the succession are therefore inverted.
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